早前寒武纪BIF原生矿物组成及演化、沉积相模式研究进展

doi:10.11867/j.issn.1001-8166.2018.02.0152

地球科学进展 ›› 2018, Vol. 33 ›› Issue (2): 152 -165. doi: 10.11867/j.issn.1001-8166.2018.02.0152

佟小雪 ^1, ^2, ³(

), 王长乐 ^1, ^2, ³, 彭自栋 ^1, ^2, ³, 南景博 ^3, ⁴, 黄华 ⁵, 张连昌 ^1, ^2, ^3, ^*(

)

1.中国科学院矿产资源研究重点实验室,中国科学院地质与地球物理研究所,北京 100029
2.中国科学院地球科学研究院(筹),北京 100029
3.中国科学院大学,北京 100049
4.深海地质与地球化学研究室,中国科学院深海科学与工程研究所,海南三亚 572000
5.中国冶金地质总局矿产资源研究院,北京 101300

收稿日期:2017-10-12 修回日期:2017-11-27 出版日期:2018-02-20
通讯作者: 张连昌 E-mail:xiaoxuetong1993@mail.iggcas.ac.cn;lczhang@mail.iggcas.ac.cn
基金资助:
国家自然科学基金项目“晚太古代清原绿岩带BIF与VMS矿床的成因联系及沉积环境”(编号:41572076);国家自然科学基金青年科学基金项目“霍邱李老庄BIF矿区磁铁矿—菱镁矿组合成因机制研究”(编号:41602097)资助

Primary Mineral Information and Depositional Models of Relevant Mineral Facies of the Early Precambrian BIF—A Preliminary Review

Xiaoxue Tong ^1, ^2, ³( ), Changle Wang ^1, ^2, ³, Zidong Peng ^1, ^2, ³, Jingbo Nan ^3, ⁴, Hua Huang ⁵, Lianchang Zhang ^1, ^2, ^3, ^*( )

1.Key Laboratory of Mineral Resources, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029,China
2.Institutes of Earth Science, Chinese Academy of Sciences, Beijing 100029,China
3.University of Chinese Academy of Sciences, Beijing 100049,China
4.Laboratory of Deep Sea Geology and Geochemistry, Institute of Deep Sea Science and Engineering, Chinese Academy of Sciences, Hainan Sanya 572000,China
5.Institute of Mineral Resources Research,China Metallurgical Geology Bureau,Beijing 101300,China

Received:2017-10-12 Revised:2017-11-27 Online:2018-02-20 Published:2018-04-02
Contact: Lianchang Zhang E-mail:xiaoxuetong1993@mail.iggcas.ac.cn;lczhang@mail.iggcas.ac.cn
About author:
First author:Tong Xiaoxue(1993-), female, Tangshan City, Hebei Province, Ph.D student. Research areas include BIF iron ore deposit.E-mail:xiaoxuetong1993@mail.iggcas.ac.cn
Supported by:
*Project supported by the National Natural Science Foundation of China “The genetic connection and depositional environment of the BIF and VMS in late Archean greenstone belt in Qingyuan, China” (No.41572076) and “The genetic mechanism of magnetite and magnesite of Lilaozhuang BIF in Huoqiu” (No.41602097)

全文 ( 13 ) 下载PDF ( 1629 )

条带状铁建造 (BIF)原生矿物组成有助于约束其沉积相和沉积环境,当前主要认为三价铁氢氧化物或铁硅酸盐微粒 (主要成分为铁蛇纹石或黑硬绿泥石) 可能是BIF原生矿物的主要成分,在后期成岩或变质作用过程中转变为赤铁矿、磁铁矿、菱铁矿等矿物。根据BIF的矿物组合可将其沉积相划分为氧化物相、硅酸盐相和碳酸盐相。通过沉积地层学和地球化学等方法研究,以古元古代大氧化事件为标志将沉积相总结为“缺氧还原”和“分层海洋”2种相模式:大氧化事件前,古海洋整体处于缺氧还原环境,BIF沉积相从远岸到近岸呈赤铁矿相—磁铁矿相—碳酸盐相分布,如南非West Rand群BIF (2.96~2.78 Ga) 和Kuruman BIF (约2.46 Ga);大氧化事件期间及之后,古海洋上部氧化、下部还原,BIF沉积相与之前截然相反,从远岸到近岸呈碳酸盐相—磁铁矿相—赤铁矿相分布,如中国袁家村BIF (2.2~2.3 Ga) 和加拿大Sokoman铁建造 (约1.88 Ga)。总体看来,只有特定的沉积环境才能形成这种特殊的地质历史上不再重复出现的沉积建造,而原生矿物组成的甄别和推导、沉积相的形成机制、BIF沉淀条件的准确限定和微生物活动与BIF的关联等问题是推测古海洋环境的关键所在,也是目前亟待解决的问题。

关键词: 条带状铁建造, 矿物成因, 原生矿物, 沉积相模式

The primary mineral compositions of BIF are regarded as ferric oxyhydroxide or iron silicate nanoparticles (mainly greenalite and stilpnomelane ) whichcan transform into minerals like hematite, magnetite and siderite. On the basis of predominant iron minerals, three distinctive sedimentary facies are recognized in BIF: oxide facies, silicate facies and carbonate facies. Marked by the Great Oxidation Event (GOE, 2.4~2.2 Ga), sedimentary facies can be divided into two models: “anoxic and reducing” model and “stratified ocean” model. The ancient ocean was anoxic and reducing before GOE, and under this circumstance, BIF was distributed from the distal to proximal zones transforming from hematite facies through magnetite facies to carbonate facies, such as West Rand Group BIF (2.96~2.78 Ga) and Kuruman BIF (~2.46 Ga) in south Africa. However, the ancient ocean was a stratified ocean during and after GOE, which means that shallow seawater was oxidizing while deeper seawater was reducing, leading to an opposite sedimentary facies distribution compared to the former one: BIF was distributed from the distal to proximal zones transforming from carbonate facies through magnetite facies to hematite facies, such as Yuanjiacun BIF in China (~2.3 Ga) and Sokoman iron formation in Canada (~1.88 Ga). Overall, BIF is an unrepeatable formation in geological history, which can only form in specific sedimentary environment. The key point to speculate the paleo-ocean environment, namely the problems to be solved at the moment, is to identify and derive the primary mineral compositions, to make sure the genetic mechanism of sedimentary facies especially silicate facies, to restrict the sedimentary conditions and to study microbial activities contacting with BIF.

Key words: Banded iron formation, Mineral genesis, Primary mineral, Depositional model.

中图分类号:

P618.31

图1 华北克拉通古元古代袁家村BIF矿物共生次序图 (据参考文献[26]修改)

Fig.1 Schematic paragenetic sequence for the Yuanjiacun BIF in the North China Craton (modified after reference[26])

图2 反射光下赤铁矿从边缘向中心逐步交代黑硬绿泥石微粒 ^{[

10
]}
(a)燧石 (ch) 条带中的黑硬绿泥石微粒 (stp);(b),(c)黑硬绿泥石微粒边缘被赤铁矿 (hem) 交代;(d),(e)赤铁矿包裹黑硬绿泥石核;(f)赤铁矿完全交代黑硬绿泥石

Fig.2 Reflected Light (RL) image showing that hematite replaces stilpnomelane microgranules from margin to cores and finally turns into solid hematite microgranules ^{[

10
]}
(a) Stilpnomelane microgranule (stp) in chert (ch). (b),(c) Stilpnomelane microgranules (stp) surrounded by thin, discontinuous rims of hematite (hem). (d),(e) Thick rims of hematite (hem) around stilpnomelane core. (f) Hematite microgranule

表1 BIF沉积相主要特征 (据参考文献[1]修改)

Table 1 Principal characters of BIF sedimentary facies (modified after reference[1])

沉积相	碳酸盐相	硅酸盐相	氧化物相
沉积相	碳酸盐相	硅酸盐相	磁铁矿亚相	赤铁矿亚相
岩石学特征	灰色,风化后呈土黄色, 燧石和碳酸盐互层	浅绿—墨绿色,不同比例的燧石、硅酸盐形成条带	深灰色,磁铁矿和燧石互层	灰黑色或灰红色,赤铁矿与灰色燧石或浅红色的碧玉形成条带
形成位置	近岸处或海底喷口附近,与碳质来源有关	一般为陆架中部,有机碳贫乏环境	深水盆地环境或陆架中部	近岸浅水处或深水有机碳贫乏环境
主要含铁矿物	菱铁矿和铁白云石等富铁碳酸盐	随变质程度的变化而不同,可能为铁蛇纹石、黑硬绿泥石、铁滑石、绿泥石、角闪石等	磁铁矿	赤铁矿
其他含铁矿物	黄铁矿、磁铁矿、黑硬绿泥石、铁滑石	含铁碳酸盐、磁铁矿	铁蛇纹石、黑硬绿泥石、铁滑石、含铁碳酸盐	磁铁矿
金属矿物含量范围	20%~35%	20%~30%	25%~35%	30%~40%
区别性特征	可见沉积缝合线构造	硅酸盐矿物种类可判定变质程度	强磁性	常见鲕粒结构
典型矿床	南非Kuruman BIF,南非West Rand 群的BIF	加拿大Michipicoten BIF, 中国鞍本地区BIF	西格陵兰Isua BIF,中国冀东司家营BIF等	西澳哈默斯利盆地BIF,中国袁家村BIF等

表1 BIF沉积相主要特征 (据参考文献[1]修改)

Table 1 Principal characters of BIF sedimentary facies (modified after reference[1])

沉积相	碳酸盐相	硅酸盐相	氧化物相
沉积相	碳酸盐相	硅酸盐相	磁铁矿亚相	赤铁矿亚相
岩石学特征	灰色,风化后呈土黄色, 燧石和碳酸盐互层	浅绿—墨绿色,不同比例的燧石、硅酸盐形成条带	深灰色,磁铁矿和燧石互层	灰黑色或灰红色,赤铁矿与灰色燧石或浅红色的碧玉形成条带
形成位置	近岸处或海底喷口附近,与碳质来源有关	一般为陆架中部,有机碳贫乏环境	深水盆地环境或陆架中部	近岸浅水处或深水有机碳贫乏环境
主要含铁矿物	菱铁矿和铁白云石等富铁碳酸盐	随变质程度的变化而不同,可能为铁蛇纹石、黑硬绿泥石、铁滑石、绿泥石、角闪石等	磁铁矿	赤铁矿
其他含铁矿物	黄铁矿、磁铁矿、黑硬绿泥石、铁滑石	含铁碳酸盐、磁铁矿	铁蛇纹石、黑硬绿泥石、铁滑石、含铁碳酸盐	磁铁矿
金属矿物含量范围	20%~35%	20%~30%	25%~35%	30%~40%
区别性特征	可见沉积缝合线构造	硅酸盐矿物种类可判定变质程度	强磁性	常见鲕粒结构
典型矿床	南非Kuruman BIF,南非West Rand 群的BIF	加拿大Michipicoten BIF, 中国鞍本地区BIF	西格陵兰Isua BIF,中国冀东司家营BIF等	西澳哈默斯利盆地BIF,中国袁家村BIF等

图3 Kuruman BIF的沉积模式 (据参考文献[67]修改)

Fig.3 Model for deposition of Kuruman banded iron formation (modified after reference[67])

图4 West Rand群中与页岩相关铁建造的沉积模型 ^{[

85
]}
反应(1)引自参考文献[45],反应(2)引自参考文献[66]

Fig.4 Simplified depositional model for the shale-associated iron formation of the West Rand Group ^{[

85
]}
Reaction (1) adapted from reference[45] and reaction (2) taken from reference[66]

图5 袁家村BIF沉积相的沉淀模型 ^{[

28
]}
反应(2)和(3)分别源自参考文献[67]和[45];反应(4)据参考文献[55]修改;反应(6)来自参考文献[66]; 反应(7)来自参考文献[86]

Fig.5 Conceptual depositional model for the Paleoproterozoic Yuanjiacun BIF ^{[

28
]}
Reactions (2) and (3) are adapted from reference [67] and [45], respectively; Reaction (4) is modifed after reference[55]; Reaction (6) is from reference[66], and reaction (7) is adapted from reference[86]

图6 加拿大Sokoman铁建造沉积相图(据参考文献[81]修改)
SWB为风暴浪基面;FWB为好天气浪基面

Fig.6 Conceptual depositional model for Sokoman iron formation in Canada (modified after reference[81])
SWB: Storm Wave Base. FWB: Fair-weather Wave Base

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